Bulletin of the Geological Society of America Vol. 69

BULLETIN OF THE GEOLOGICAL SOCIETY OF AMERICA VOL. 69. PP, 316-342. 8 FIGS.. 8 PUS. MARCH 1968

STRATIGRAPHY OF THE COW HEAD REGION, WESTERN NEWFOUNDLAND

BY C. H. KINDLE AND H. B. WHITTINGTON

ABSTRACT Seashore exposures in the Cow Head area display a succession of limestone conglomerates interbedded with shales and limestones. Conglomerate layers range in thickness from 1 foot to more than 200 feet. The material consists of flat angular chips or moder- ately rounded boulders of fine-grained gray or white limestone. Fossiliferous boulders from any one layer yield trilobites of the same limited age. Boulders from the lowest fossiliferous conglomerate at Broom Point contain Kootenia, Zacanthoides, Orriella, Agraulos, and Peronopsis. Succeeding bedded limestone yields Meneviella and Tomagnostus. A boulder in the overlying conglomerate also contained Meneviella and Tomagnostus. Cambrian conglomerates at Cow Head yield younger trilobites in successive layers: Tricrepicephalus appears in the lower, then Taenicephalus, followed by Ctenopyge, Ra- settia, and Keithietta. Above are beds with Staurograptus and Dictyonema, overlain by conglomerates with early Ordovician trilobites. Successively higher black shales contain graptolites of the Levis Shale zones, and interbedded conglomerates yield successively younger Ordovician trilobites. Shale with Tri- gonograptus and Isograptus underlies the highest conglomerate which yields Ntteus, Bathyurellus, Remopleurides, and Ectenonotus. The thick limestone conglomerate at Lower Head includes enormous boulders, one of which contains many of the trilobites described by Billings (1861-1865) as from Cow Head. This layer is underlain by black shale with Isograptus. The Cow Head Group, therefore, is not a single formation but a succession of conglomerates and intervening beds ranging in age from Middle Cambrian to Middle Ordo- vician. With few exceptions the boulders of any conglomerate are approximately the same age as the immediately underlying strata. The limestones of the fossiliferous boulders formed in shallow water; the beds intervening between the conglomerate layers formed in deeper water and consequently are almost devoid of fossils other than graptolites.

CONTENTS TEXT ILLUSTRATIONS Page Figure Page Introduction and acknowledgments 316 \ J^aP sh™ing ****** of Cow Head rfgion • 3^ General statement on stratigraphy 316 \ Geological map of Coww Head peninsula.... 320 Details of stratigraphy 319 4 stratigraphic columns 321 V^UPnwW ilctlHparQl r«>nin«aiipclllIlSUlcal Ol310" - Ordoviciai .• n of Cow Head region and its cor- •JTQ c*- Pfl.ipo tnlpt l?f\ relation Jzo Martin Point 330 5' Ordovician sections, St. Paul's Inlet 329 6 Sect on at Martin Po int 33 Green Fob? ^33321 ^'- Sectio! n at Broom Poin. t 33° 3 •22T 8. Rocks of Lower Head 335 OJ4 White Rock Islets 333 Plate Following page Lower Head 334 1. Cow Head Group on Cow Head... Discussion of stratigraphy 335 2. Cow Head Group on Cow Head. Nomenclature of Cow Head Group 335 3. Cow Head Group on Cow Head, and ex- Zonation and correlation with other areas... 337 posures at Green Point. P. 322 Relation of Cow Head Group to other se- 4. Boulder in bed 6, Cow Head, and con- quences 339 glom erate at Lower Head J Origin of the conglomerates 340 5. Ordovician beds at Martin Point and Lower References cited 341 Head 326 315

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Plate Following page TABLES 6. Ordovician conglomerate, Cow Head and Table Page Lower Head 1. Stratigraphical classification in the Cow 7. Contemporaneous deformation at Green!- 326 Head region 317 Point j 2. Correlation of Cambrian faunas of the Cow 8. Middle Cambrian beds at Broom Point. . . J Head region 319

INTRODUCTION AND ACKNOWLEDGMENTS The Geological Society of America for grant 671-55 of the Penrose Bequest which enabled Schuchert and Dunbar (1934) provided the them to undertake the field work. Whittington foundation on which geologic mapping in received a grant from the Harvard Foundation western Newfoundland was conducted by the for Advanced Study and Research which made Geological Survey of Newfoundland for the it possible for him to study type specimens of next 12 years. In 1938, 1939, and 1945 Kindle trilobites described by Billings (1861-1865), was invited to assist Dr. Helgi Johnson in this through the kind permission of Dr. H. Frebold work. Limestone conglomerates encountered at the Geological Survey of Canada, Ottawa. were regarded, in part, as puzzling thrust The hospitality and assistance of many breccias. friends in western Newfoundland, and Mrs. In 1952 Kindle again visited the Cow Head Whittington's contributions to the fossil collec- area to assemble dip and strike data for the tion are gratefully acknowledged. John Fox iil drilling interests. These data indicated an orderly arrangement in the supposedly GENERAL STATEMENT ON STRATIGRAPHY chaotic Cow Head "breccia." In the same year Philip Oxley of the Geological Survey of New- Schuchert and Dunbar (1934) described the foundland discovered a layer of Middle Cam- outcrops on Cow Head peninsula and adjacent brian agnostids at Broom Point in a block areas in detail, and "were forced to interpret which had fallen from strata between layers of these lenticular masses of coarse breccia as the limestone conglomerate. This led to the realiza- materials of talus and landslides formed along a tion that some of the Cow Head conglomerates fault scarp that came into existence during must be Middle Cambrian. Oxley also found Mid-Ordovician orogeny" (p. 84). They also Endymionia, a Table Head trilobite, in thin- recognized that a sequence of shales, silt- bedded limestones below limestone conglom- stones, and limestones cropped out at Martin erates at the Inner Tickle of St. Paul's Inlet. Point, Broom Point, and St. Paul's Inlet but Thus some of the limestone conglomerates considered that this sequence belonged to the must be Middle Cambrian, others Middle Green Point Series of earliest Ordovician age Ordovician. A reinvestigation of the stratig- and was older than the St. George Series raphy of the conglomerates and associated (Table 1; Schuchert and Dunbar, 1934, p. 39). strata in the Cow Head area is necessary to Johnson (1941) was the first to show that provide a secure foundation for proposed these rocks were, in the Cow Head region, faunal studies. Lower and Middle Ordovician and thus a Accordingly the writers spent 7 weeks in different facies from the St. George and Table 1955 in western Newfoundland. On Cow Head Head Series. He proposed two new strati- peninsula and at near-by exposures abundant graphical names (Table 1) and commented evidence was found that the Cow Head lime- that there were several horizons of intraforma- stone conglomerates range from Middle Cam- tional conglomerates as well as the Cow Head brian to Middle Ordovician. The structure and breccia (1941, p. 143). stratigraphy of Cow Head peninsula are so at Oxley (1953) published the first detailed map variance with published views that a prelim- of the region between Portland Creek Pond and inary report is advisable. The identifications of Martin Point, using a combination and emenda- fossils herein are preliminary, and the faunas tion of earlier Stratigraphical divisions (Table will be described in detail in a later publication. 1). He recognized two facies in the Lower Detailed topographical maps of the region Ordovician—the Green Point-St. Paul Group are not available, but the Hydrographic Office and the St. George-Table Head Group—and charts are useful for the coastal regions. Aerial regarded the Cow Head Breccia as overlying photographs, scale 2 inches to 1 mile, are both. obtainable from the National Air Photo The 1954 map of the Newfoundland Depart- Library in Ottawa, Canada. ment of Mines and Resources, Mines Branch, The writers are indebted to the Council of Geological Survey shows undifferentiated

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Ordovician rock in this area; the 1955 map of Cambrian to Middle Ordovician time. Oxley the Department of Mines and Technical Sur- (1953, p. 11) was the first to list Middle Cam- veys, Geological Survey of Canada leaves the brian trilobites from this region. These are area blank. Fossils from the Cow Head region said to come from a boulder in a conglomerate

TABLE 1.—STEATIGRAPHICAL CLASSIFICATION IN THE Cow HEAD REGION Schuchert and Dunbar (1934) This Lochman (1938) Johnson (1941) Oxley (1953) paper

c Humber Arm Series Un- Cow Head Breccia Humber Arni Group Humber Arm Group named Long Point Series Cow Head Breccia green Middl e rdovici a Table Head Series Portland Head St. Paul's sand- 0 Group Group stones St. George Series Table Head Western Table Head St. Paul 'G Group Brook St. George Green Pond Group Point -ao O Group Group Cow Green Point Series St. George Green o Group Point Group Head ac ' O 1-1 G -g Petit Jardin Formation ? Group

| s March Point Formation ? P

have been listed by Schuchert and Dunbar but actually came from a block of the bedded (1934), Kindle (1943), Ruedemann (1947), and limestone which had fallen to the shore. The Oxley (1953). Descriptions of Cambrian and writers found Middle Cambrian trilobites in Early Ordovician trilobites have been published bedded limestones and also in conglomerate by Billings (1861-1865), Raymond (1925), boulders. Upper Cambrian trilobites have been Lochman (1938), Kindle (1942; 1948), and found only in boulders in younger conglomerate Rasetti (1954). layers. In the Ordovician part of the sequence The writers believe that on Cow Head the writers established a zonal sequence of peninsula and certain adjacent coastal regions graptolites from finds of these fossils in the (Fig. 1) a sedimentary series ranging from bedded shales and dark limestones. The suc- Middle Cambrian to Middle Ordovician is cessively younger interbedded conglomerates exposed. This group of strata is about 1000 have yielded an orderly succession of trilobite feet thick, consisting of thin-bedded limestones faunas. The late Middle Cambrian to Middle with shale partings and interbedded shales, Ordovician part of the sequence is exposed and, rarely, sandstones; at intervals throughout along the shores of Cow Head peninsula. Older the sequence occur spectacular beds of lime- Middle Cambrian conglomerates crop out on stone conglomerates. Some of the boulders and the neighboring White Rock Islets but are best blocks in these conglomerates are fossiliferous, displayed at Broom Point, 6 miles to the south- and in any one layer are all about the same age southwest. Pending further studies which may The beds on which a particular conglomerate give a more detailed picture of the stratigraphy, layer rests are about the same age as the blocks it seems simplest to use the name Cow Head in the overlying conglomerate. This is true Group (an emendation of Schuchert and throughout the sequence, and thus these con- Dunbar's Cow Head Limestone Breccia) for glomerate layers are intraformational and were this Middle Cambrian to Middle Ordovician brought into place periodically during Middle sequence, rather than to introduce new names.

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The Cow Head Group, like the Table Head and trilobite faunas enables the writers to make Series, is overlain by a clastic sequence with a tentative correlation between zones estab- characteristic greenish sandstones. The writers lished on these two groups. Two and perhaps have not studied these rocks in detail and have three facies can be recognized during Cow Head

FIGURE 1.—MAP SHOWING LOCATION OF Cow HEAD REGION In St. Paul's Inlet A shows location of Green Island (Late Cambrian); B and C show locations of Figures SB and 5A; and D shows location of White Point (Middle Cambrian). not used either an old or a new name in referring Group time in western Newfoundland, but the to them (Table 1). spatial relationship of these facies cannot yet be The limestone conglomerates of the Cow clearly portrayed. The earliest folding and Head Group, both physically and in their thrusting for which there is clear evidence in faunas, are remarkably like those of Le vis and the Cow Head region is post-Cow Head Group, other localities along the south shore of the St. i.e., later than early Middle Ordovician. Earlier Lawrence River. Both the Cambrian and tectonic activity must have produced the blocks Ordovician trilobites in these conglomerates in the conglomerates and the submarine slopes show affinities with those of near-by areas as well as with Utah and Nevada and with Europe. down which they moved into place in the Cow This mixture of Atlantic and Pacific faunas Head Group. Since rocks older than Middle affords new correlation possibilities. The Cambrian were not encountered in the shore Ordovician graptolite zones are like those of exposures Table 1 does not include the Lower southern Australia, rather than those of western Cambrian formations that occur a few miles Europe. This unique alternation of graptolite inland.

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TABLE 2.—CORRELATION or CAMBRIAN FAUNAS or THE Cow HEAD REGION

Equivalent American Cambrian faunas of faunal zones the Cow Head area Occurrence Equivalent Swedish faunal zones

Theodenisia Zone 5 of the Olenid Series (with c Rasettia Ctenopyge} Hittigaia magnifica Plethometopus Bed 6 ,0p fauna Keithiella Cow Head cS (Trempealeauian) o Loganopeltoides Ctenopyge • 0). Taenicephalus sub-zone Taenicephalus Bed5 ? Zone 4 of the Olenid Series (Franconian) Parabolinella Cow Head

Coosella STAGE OF PARADOXIDES CatHlicephala FORCHHAMMERI Paradoxides forchhammen Deirocephalus zone Hemirhodon Beds 1, 3, 4 Zone C3 — Lejopyge laevigata Kingstonia Cow Head (Dresbachian) Meteoraspis Zone C2 — Solenopleura brachyrnelopa Tricrepicephalus Zone Cl — Ptychagnostus lundgreni c Paradoxides davidis STAGE OF PARADOXIDES zone PA RA DOXISSIM US 1d= Broom QJ Hypagnostus Zone B4 — Ptychagnostus punctuosus T3 Point 3 Paradoxides hicksi Peronopsis zone Meneviella Zone B3 — Hypagnostus parmfrons Tomagnoslus fissus Zone B2 — Tomagnostus fissus Zone Bl — Ptychagnostus gibbus Agraulos Broom Orriella Point Kootenia and Zacanthoides White Rock Peronopsis Islets 1 gibbus

DETAILS or STRATIGRAPHY the axes of which trend about N. 15° E. and are Cow Head Peninsula cut by normal faults of small displacement. The northeastward-trending normal fault at the The writers' observations on Cow Head northeast tip of the peninsula is shown in peninsula are summarized in the map (Fig. 2), Schuchert and Dunbar (1934, PI. 10B). Another the columns (Fig. 3), and in Table 2. The such fault on the southeast shore (not indicated writers believe that the peninsula shows a con- on Figure 2), which cuts beds 8d (limestone formable series of interbedded limestones, and shale) and 8e (conglomerate), is figured by shales, and conglomerates, about 800 feet thick. Schuchert and Dunbar (1934, Plate 9B) and From bedded limestones of bed 3, cropping out shows a relative downward displacement of on the northeast shore, come fossils of Dresbach the conglomerate on the west (right side of the age (equivalent to the Paradoxides forchham- figure). meri zone) and from black shales of bed 13, on The oldest stratum on the peninsula seems to the southwest shore, come graptolites of early be the conglomerate layer 1 which forms the Middle Ordovician age. The rocks of the penin- outer edge of the point northwest of Tucker's sula are folded into a syncline and an anticline, Cove and is also exposed at low tide in Beachy

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Cove. This layer is at least 6 feet thick and with the bedding in the blocks usually bent or contains many limestone boulders up to 3 feet thrown into folds. The conglomerate is shown in size. From some of these boulders the writers in Schuchert and Dunbar (1934, PI. 9A). The obtained Tricrepicephalus sp., Crepicephalus writers found fossils similar to those obtained sp., and Deiracephalus sp. Bed 1 is cut off on by Schuchert and Dunbar (Lochman, 1938, p. the east by a northeastward-trending fault. 463-464) in the bedded portions and conglom- East of this fault, at the northwestern end of erate blocks of bed 3. These include Meteoraspis Tucker's Cove, the following descending sec- sp., Catillicephala sp., Kingstonia sp., Blountia tion, dipping about 20° to the south is exposed sp., Tricrepicephalus sp., and Coosella sp. Loch- on the shore and in the cliffs: man (1938) considered them to belong to the Crepicephalus zone of the Dresbach. The latter Feet stage is now regarded as late Middle Cambrian c. 15 Limestones and shales and interbedded 2-foot layers of flat pebble conglomerate. Rounded (Lochman, 1956, p. 447). quartz grains occur in the matrix of some of Bed 4 is visible on the shore west of Beachy these conglomerates. Cove, near a path that descends the cliff. It is a c. 90 Shales and limestones with some conglomerate conglomerate with boulders up to S feet in lenses. These strata are shown in Schuchert and Dunbar (1934, Pis. 10A and 10B, left diameter. Several smaller boulders proved side). abundantly fossiliferous, and from them the c. 28 Calcareous sandstone with some conglomerate. writers identified: Catillicephala sp., Coosella c. 15 Coarse limestone conglomerate, boulders up sp., Kingstonia sp., Ithycephalus sp., Tri- to 3 feet in maximum dimension. c. 3 Shale. crepicephalus sp., Meteoraspis sp., Bienella sp., Up to 30 feet of limestone conglomerate ex- Millardia sp., and Deirocephalus sp. These posed east of the fault, boulders up to 3 feet. boulders are apparently of about the same age as those of bed 3. Higher beds in this section are concealed by Bed 5, separated from bed 4 by a 1-foot band the sandy beach of Tucker's Cove, but if this of shale and limestone, includes 60-70 feet of section is continuous with that on the southeast limestone conglomerates predominantly of side of the cove, then, judging by thicknesses, small, flat chips, with scattered larger boulders the lower beds must be about the same age as up to about 3 feet in length. This bed forms a bed 1 but might be slightly older. No fossils were rampart for more than a quarter of a mile found in the bedded strata, and the conglomerates were not searched intensively. along the northwest shore. Several of the Beds 2 and 3 are well exposed in Beachy Cove. larger boulders were highly fossiliferous. The The former is a flat pebble conglomerate from following occurred in a boulder 30 feet from the which no fossils were obtained. Bed 3 may be sea in front of the lighthouse: Taenicephalus seen along the foot of the cliff at Beachy Cove; sp., Parabolinella sp., and Pseudagnostus cf. in places it consists entirely of thin-bedded gyps. From a boulder much farther west and limestones, and in other places these limestones nearer the top of the bed the writers collected pass laterally into limestone conglomerate (PI. Onchonotus sp., ? Aposolenopleura sp., Tal- 1, fig. 1). The conglomerate includes large botina ? levisensis, Loganopeltoides sp., and blocks of thin-bedded, greenish limestones Pseudagnostus cf. gyps. Taenicephalus is charac-

PLATE 1.—COW HEAD GROUP ON COW HEAD FIGURE 1.—Bed 3, cliff at Beachy Cove, Cow Head peninsula, showing bedded limestones passing laterally into conglomerate. FIGURE 2.—Looking south across The Ledge, southwest tip of Cow Head peninsula. Arrows point to base of conglomerate bed 12, which cuts downward across bed 11.

PLATE 2.—COW HEAD GROUP ON COW HEAD FIGURE 1.—Cliff at Crow's Nest, looking southeast from the sea off Cow Head peninsula. Bed 7 (with large boulders) runs diagonally up the cliff, which is about 100 feet high. Sea is breaking against bed 5, behind which the lower part of bed 6 is concealed. FIGURE 2.—Shore west of lighthouse, Cow Head peninsula, looking northeast. Sandstone rib in bed 6 is to right of center; base of bed 7 is in cliff.

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COW HEAD GROUP ON COW HEAD

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------COW HEAD GROUP ON COW HEAD

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------COW HEAD GROUP ON COW HEAD AND EXPOSURES AT GREEN POINT

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BOULDER IN BED 6, COW HEAD, AND CONGLOMERATE AT LOWER HEAD

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teristic of the Conaspis zone of the Franconian Succeeding bed 6 is a prominent band (bed Stage of the Upper Cambrian. 7), 30-50 feet thick, of conglomerate with many Bed 6 forms the lower ground between the large boulders up to 6 feet in length. Some of the wall made by bed 5 and the base of the cliff and large boulders are brown limestone, but many extends up the lower part of the cliff (PI. 2, fig. are white limestone. Consequently bed 7 is 2). The greater part of the bed is thin-bedded conspicuous where it runs along the top of the limestones and shales, but there are lenses of cliff at Crow's Nest (PL 2, fig. 1) and out to conglomerate of small flat limestone chips and a Point of Head. As seen in this cliff the con- few boulders. An 8-foot layer of limy sandstone glomerate rests on a slightly uneven base on the with rounded quartz grains occurs near the thin-bedded limestones, and in places these middle of bed 6 and forms a conspicuous rib limestones are disturbed or broken, which sug- running along the shore. Similar sand grains in gests that they were torn up as the conglomer- the matrix of the conglomerates and forming ate was deposited. Southwest of the lighthouse calcareous sandstones occur throughout the the outcrop of bed 7 swings inland and is seen in upper half of bed 6; sandstones associated with the prominent cliffs that run east-southeast the higher conglomerate form a second con- across the peninsula south of the lower ground spicuous rib (PI. 3, fig. 1). These sandstones behind the village. Apparently the same band were noted by Schuchert and Dunbar (1934, p. reappears on the southeast side of Tucker's 76). The position of the ribs is indicated on the Cove and again forms a conspicuous rib of map (Fig. 2). Figure 1 of Plate 4 shows an large white and brown boulders. Fossils were isolated boulder of light limestone resting in obtained from white limestone boulders at thin limestone and shale of the upper part of three places: bed 6 near the base of the cliff. Smaller boulders Near Point of Head : similarly situated were observed near by. Fossils in the few larger boulders in conglom- Keithia sp. erates in the upper part of bed 6 (PI. 2, fig. 2) Theodenisia sp. were of one fauna: Ctenopyge cf. flagellifera, Rasettia sp. Theodenisia sp., Rasettia sp., Keithia sp., cf. Bayfieldia sp. Keithiella sp., Plethometopus sp., ? Loganopel- Sterwpilus sp. toides sp., and ? Loganellus sp. All these trilo- Leiocoryphe sp. bites except Ctenopyge are present in Upper Plethometopus sp. Cambrian faunas from the boulders of the ? Phoreotropis sp. Levis Formation (Rasetti, 1944, 1945), and ? aff. Loganellus sp. similarity in age is indicated. From thin- From one boulder at the top of the cliff near the bedded limestones with shale partings 3-5 feet center of the peninsula, about half a mile west below the top of bed 6 the graptolites Stauro- of the village: graptus sp. and Dictyonema sp. were collected; these are characteristically Early Ordovician Pardbolinella sp. (i.e., Tremadoc or lowest Lancefield Series of Symphysurina sp. Victoria). No fossils were found in the lime- Rasettia sp. stone and conglomerates of bed 6 which crop Pseudohystricurus sp. out on the southeast side of Tucker's Cove. BieniiUlia sp.

PLATE 3.—COW HEAD GROUP ON COW HEAD AND EXPOSURES AT GREEN POINT FIGURE 1.—North side of Point of Head, looking southwest, Cow Head peninsula. Upper part of bed 6 with sandstone rib; bed 7 forms cliff. FIGURE 2.—Section at Green Point. Arrow indicates fossiliferous Green Point Formation.

PLATE 4.—BOULDER IN BED 6, COW HEAD, AND CONGLOMERATE AT LOWER HEAD FIGURE 1.—Isolated limestone boulder in thin-bedded limestone of upper part of bed 6, foot of cliff below lighthouse, Cow Head peninsula. FIGURE 2.—West side of tip of Lower Head, looking south. In left foreground is part of large block of white limestone with surrounding conglomerate to right; arrows point to edge of large block. In right back- ground is Cow Head peninsula.

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From the southeast side of Tucker's Cove: ders of Upper Cambrian age, but of the fossils from the higher level only Stenopilus occurs in Lloydia sp. the same Levis boulders. Symphysurina and Leiostegium sp. Hystricurus are Lower Ordovician in age, and Rasettia sp. the suggestion is that the material forming the Keitltia sp. conglomerate is of about this age and was laid Stenopilus sp. down during this time. ? Onchonotus sp. Bed 8 also crops out between Tucker's Cove ? Hystricurus sp. and Little Cove and along the shore between cheirurid of Parapilekia type the sand bar linking the peninsula to the main- land and Shoal Cove (Fig. 2). Above bed 7 on The fauna from Point of Head is of the the southeast side of Tucker's Cove is 8 feet of Hungaia magnified zone of boulders in the limestone conglomerate of small chips, suc- Levis conglomerate (Rasetti, 1944, 1945), ceeded by about 85 feet of thin-bedded brown regarded by Rasetti as late Upper Cambrian limestone with shale partings. Southwest of (Trempealeau) age but by Shaw (1955) as here, at the base of the sand bar, continuous "probably Franconian." Faunas from the other exposures of higher beds are seen. The altera- boulders show a mingling of some of these tions of coarse boulder conglomerates, flat Levis fossils with genera commonly regarded pebble conglomerates, shales, and limestones as Early Ordovician, including Symphysurina, with shale partings have been subdivided for Pseudohystricurus, Lloydia, and Leiostegium. convenience (Figs. 2, 3). The contrast in The strata immediately below bed 7 are Early lithology between the sections in beds of the Ordovician and thus at least some of the same age at opposite ends of the peninsula boulders in the conglomerate were formed shows how rapidly lateral variations may occur. penecontemporaneously with the beds on which Bed 8a is a coarse conglomerate with many it rests. Even if the boulders with the Hungaia boulders of mottled white and light-gray fine- fauna are regarded as older and of Upper Cam- grained limestones up to 2 or 3 feet in length, brian age, at least some of the elements in this and a few chert boulders. Few fossils were fauna may range into the Lower Ordovician. found in these boulders; among them were The Tremadoc fauna described by Shaw (1951; trilobite fragments representing ? Bellefontia 1955) from northwestern Vermont includes sp. Trilobites from one boulder in the second Parabolinella and Symphysurina, but the other conglomerate above bed 8a, here called 8e, species do not resemble those from Newfound- include the Upper Cambrian Levis boulder land. genera Keithiella, Rasettia, Leptopilus and cf. Point of Head is formed not only by bed 7 Onchonotus; from three or four large boulders a but by 150 feet of overlying conglomerate, number of typical Canadian genera included: here called bed 8. Most of this bed is composed of small flat chips of limestone in a fine-grained Trinodus sp. matrix, but lenses of coarser conglomerates cf. Protopresbynileus occur, and in the upper part are layers of a few asaphid feet of thin-bedded limestone. Blocks of lime- remopleuridid, n. gen. stone 2 to 4 feet in length occur rarely, but at Petigurus sp. most levels, in the chip conglomerates. Fossils illaenids (2 species) obtained from boulders in a coarse layer about aff. Goniophrys 30 feet below the top of bed 8 include Sym- Ampyx sp. physurina sp., Stenopilus sp., Hystricurus sp., cf. Glaphurina and Pseudagnostus sp. This layer contained ? Selenoharpes many boulders of white and brown fine-grained pliomerid limestone, some 4 feet in length. Similar blocks occur in the lower 100 feet of bed 8, but most From boulders in bed 8g came similar Canadian were unfossiliferous. From one or two such trilobites: blocks were obtained cf. Theodenisia sp., Plethometopus sp., ? Stenopilus sp., ? Sym- cf. Protopresbynileus physurina sp., and Rasettia sp. aff. Benthamaspis All these trilobites except ? Symphysurina illaenid are known from the Levis conglomerate boul- Ampyx sp.

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and from the shale partings in the limestones approximatus (Nicholson), T. quadribrachiatus below (bed 8f) the graptolites (Hall), and Didymograptus cf. hirundo Salter. These shales also represent the basal part of Dictyonema sp. bed 9. In the upper part of bed 9 near The Clonograptus fiexilis (Hall) Ledge T. quadribrachiatus and Dictyonema sp. C. rigidus (Hall) occur in shale partings. Tetragraptits approximate (Nicholson) Bed 10 is a coarse conglomerate 4-8 feet T. quadribrachiatus (Hall) thick where it crops out on the north side of the Phyllograptus ilicifolius Hall Ledge and up to 20 feet thick where it runs along the low cliff in Shoal Cove. At this latter These graptolites are those of the earliest place some rounded or flat boulders up to 10 Levis shales, Raymond's (1914) zone A, and are feet in length consist primarily of fine-grained older than any known in the type Deepkill limestone. Some boulders are of interbedded section (Ruedemann, 1947, p. 281, 313). In shale and limestone. Fossils collected from two Australian terms they seem to be of high boulders included ? Trinodus sp., a ribbed Lancefield age, approximately equivalent to asaphid pygidium, cf. Protopresbynileus sp., ? zone La3 (Harris and Thomas, 1938). The Petigurus sp., Ampyx sp., a raphiophorid, n. trilobites from 8e are clearly older than this gen., and cf. Ectenonotus sp. A large collection but cannot be closely compared with those was also made from a loose boulder on the shore, from Utah or Nevada described by Ross (1951) on the east side of Shoal Cove and near the and Hintze (1952). Judging by trilobites in place where bed 10 appears to be displaced by a older and younger conglomerates, those from normal fault. This boulder may be from bed 9 8e are probably from a horizon within the or bed 10, probably the latter. It contained Ross-Hintze zones B to E. Unfortunately the Protopresbynileus sp., a remopleuridid, n. gen., exact position from which Clonograptus flexilis cf. Petigurus, Bolbocephalus sp., an illaenid, aff. came in the Logan, Utah, area (Clark, 1935) is Benthamaspis sp., cf. Psalakilus sp., aff. unknown. The cranidium listed as cf. Glaphur- Goniophrys sp., Ampyx sp., a harpid, and a ina sp. is remarkably like that of G. f insolita pliomerid. recently described by Tjernvik (1956) from the Comparisons with Ross' (1951) and Hintze's early Arenig of Sweden. The general aspect of (1952) work suggest that the trilobites from these trilobites from bed 8e is of a post-Tre- madoc age, and accordingly they and the bed 10 and the loose block may be from a zone Telragraptus approximatus graptolite zone are approximately the same as their zones G and regarded as of early Arenig age. H. Bed 10 could not be recognized in the shales Bed 9 is best seen at the southwest tip of the and limestones exposed in the next cove south- peninsula, between Point of Head and The west of Shoal Cove. Immediately overlying Ledge. It includes thin-bedded limestones, bed 10 at Shoal Cove and The Ledge are layers shales, and lenses of limestone conglomerate. of black chert which are weathering brown, Near the base, just above the great thickness of followed by shales and thin limestones. From conglomerates forming Point of Head, shale the shale just above the chert at The Ledge partings in dense limestones yielded Clono- came Dichograptus octobrachiatus (Hall), Goni- graptus cf. rigidus (Hall), Tetragraptus approxi- ograptus thureaui (McCoy), Tetragraptus fruti- matus (Nicholson), and T. cf. quadribrachiatus cosus (Hall), Didymograptus of extensiform (Hall). type, and Phyllograptus cf. anna Hall. In These beds are of about the same age as bed Shoal Cove the shales yielded Tetragraptus 8f in Cow Cove but higher beds there, shale fruticosus (Hall), T. serra (Brongniart), and partings in thin limestones immediately below Phyllograptus sp. the coarse conglomerate bed 9, contain T. approximatus, T. quadribrachiatus, and Ptilo- These beds are thus of the same age as graptus sp. These latter are regarded as the Raymond's (1914) zone B of the Levis shale, basal part of bed 9 in this vicinity. On the west the lowest part of the Deepkill shale (zone 1 side of Shoal Cove a normal fault trends north- of Ruedemann, 1947, p. 61), and the lower part westward (Fig. 2), and west of it are black and of the Bendigo Series of Victoria, Australia gray shales interbedded with limestones, under- (Harris and Thomas, 1938). lying 6 feet of coarse limestone conglomerate. Bed 12 consists of about 20 feet of coarse The shales contain the graptolites Tetragraptus limestone conglomerate, well exposed on the

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east side of Jim's Cove and as it runs out to 30-50 feet thick. Large blocks of white and of The Ledge. At the latter locality, as the base is brown limestone, including one of white lime- followed landward, it transgresses downward stone 75 feet in length and one 20 feet long of over the thin limestones and shales of bed 11, limestone and shale may be seen, especially on cutting across 15 feet of stratigraphical thick- the west side of Deep Cove. Numerous blocks ness in 30 yards along the strike (shown in of this latter type are contorted, with ragged part in PL 1, fig. 2). Several boulders at least edges projecting into the surrounding fine- 10 feet in length are seen near the base of this grained matrix and pebbles (PI. 6, fig. 1). From bed and give the appearance that this con- several boulders of gray limestone the following glomerate plowed into the underlying shale fossils were obtained: Nileus sp., Presbynileus as it was being laid down. Fossils from one sp., Remopleurides sp., an illaenid, Bathywellus boulder in bed 12 at The Ledge include an sp., Ampyx sp., Raymondaspis sp., a harpid, agnostid, Nileus sp., an illaenid, Telephina sp., a ceraurid, and Ectenonotus cf. westoni (Bill- and Kawina cf. vulcanus (Billings). ings). From a single boulder of white limestone Nileus and Kawina appear in strata of the was collected "Illaenus" cf. tumidifrons Bill- Whiterock Stage (Cooper, 1956) in Nevada, ings, cheirurid cf. "Cheirurus" prolificus Bill- and Nileus and Telephina are well known from ings, and "Lichas" jukesi Billings. the Table Head Series of the same stage (Ray- These last three species are similar to, or mond, 1925, p. 65-66, 83-85), as well as from identical with, those described by Billings from younger rocks in Virginia. The type species of the gigantic boulder of white limestone at Kawina, K. vulcanus came from the enormous Lower Head, in a conglomerate believed to be boulder of white limestone in the conglomerate of the same age as bed 14. The assemblage from at Lower Head, which is probably the same as bed 14 is typical of the Table Head Limestone. the conglomerate layer on Cow Head that is (Cf. Schuchert and Dunbar, 1934, p. 68-69.) here called bed 14. The age of these trilobites Whittington collected species of Ectenonotus seems to be earliest Middle Ordovician, i.e., and Nileus from the Orthidiella zone of the type Whiterock Stage. Whiterock Stage in Nevada. In terms of Ross' The highest beds on Cow Head peninsula are (1951) and Hintze's (1952) work in Utah and the shales and thin limestones of bed 13 and the Nevada this assemblage has some affinities conglomerate on either side of Deep Cove, bed with their highest zones, M and N, but may be 14. Black shales 3 feet below the base of bed somewhat younger than zone N. 14 on the west side of Deep Cove contained Tetragraptus cf. serra (Brongniart), Goniograp- St. Paul's Inlet tus sp., Didymograptus sp., Isograptus caduceus cf. maxim o-diver gens Harris, and Trigonograptus St. Paul's Inlet (Fig. 1) may be entered cf. ensiformis (Hall). through a narrow channel in the relatively This fauna is like that of Raymond's (1914) wide mouth immediately south of St. Paul's zone Di of the Levis Shale, the highest Deepkill Point—the Outer Tickle. A narrow entrance, Shale, and late Castlemain or early Yapeen the Inner Tickle, leads from a shallow bay into Series of Victoria, Australia. T. cf. serra and 7. the inlet proper. A section (Fig. 5B) is exposed caduceus were also found in the folded lime- along the inner, east side of the northern prom- stones and shales of bed 13 visible at low tide ontory forming the Inner Tickle and is the in Jim's Cove. The conglomerate of bed 14 is upper part (units 14-27) of that measured by

PLATE 5.—ORDOVICIAN BEDS AT MARTIN POINT AND LOWER HEAD FIGURE 1.—North of hogback forming point south of Martin Point. Thin-bedded Lower Ordovician limestones and shales overlain by disturbed beds of similar type which pass upward into conglomerate. FIGURE 2.—Limestone conglomerate at Lower Head resting above shale (at A in Fig. 8).

PLATE 6.—ORDOVICIAN CONGLOMERATE, COW HEAD AND LOWER HEAD FIGURE 1.—Edge of block of folded thin-bedded limestone, in conglomerate bed 14, west side of Deep Cove, Cow Head peninsula. Hammer lies across boundary between block and surrounding conglomerate of smaller pebbles. FIGURE 2.—Limestone conglomerate on west side of point of Lower Head.

------ORDOVICIAN BEDS AT MARTIN POINT AND LOWER HEAD

------

------ORDOVICIAN CONGLOMKRATE, C.OW HEAD AND LOWER HKAD

------

------CONTIOMPOHANKOUS DKFORMATION AT GHKKN POINT

------

------MIDDLE CAMBRIAN BEDS AT BROOM POINT

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Oxley (1953, p. 22-24). Graptolites were col- Harris, I. caduceus cf. var. maximo-divergens lected at the following points, which are indi- Harris or var. armatus Ruedemann, and Didy- cated on Figure 5B: mograptus sp. From the limestones Oxley (1953, (1) From dark shales interbedded with cherts p. 22) records the Table Head trilobite, Endymi- resting on limestone conglomerate (Oxley's onia schucherti Raymond, and a large linguloid unit 14): Clonograptus rigidus (Hall), Tetra- brachiopod. The graptolites are characteristic graptus approximate (Nicholson), and T. of the Castlemain Series of Australia (Harris quadribrachiatus (Hall). These graptolites are and Thomas, 1938). characteristic of Raymond's (1914) zone A of Kindle collected graptolites at two localities the Levis Shale, and of the upper Lancefield near Black Brook (Fig. 5.4). At the tip of the Series of Victoria, Australia (Harris and point west of the mouth of Black Brook he Thomas, 1938). found Dictyonema sp., Clonograptus flexilis (2) From dark shales succeeding a conglom- (Hall), Phyllograptus cf. ilicifolius Hall, and erate band, about 80 feet above (1): Tetragrap- Didymograptus sp. Phyllograptus is abundant, tus fruticosus type with three stipes, T. cf. and the extensiform didymograptids are large. serra, Phyllograptus typus, and Didymograptus Bryograptus is absent. The assemblage is thus "bifidus" cf. Ruedemann (1947, PL 54, fig. 15). like that of the Tetragraptus approximatus zone The occurrence of T. fruticosus with appar- rather than that of the zone below. ently only three pendant stipes (not four as in In dark shales interbedded with green sand- the typical form) suggests a correlation with stones and red shale, just west of the mouth of the upper half of the Bendigo Series of Aus- Black Brook and about 275 feet higher in the tralia (Harris and Thomas, 1938). Specimens section, were found Isograptus caduceus cf. var. identified as D. bifidus occur in zone 2 of the divergens Harris, Tetragraptus cf. bigsbyi, and Deepkill Shale (Ruedemann, 1947) and in Didymograptus sp. zone C of the Levis Shale (Raymond, 1914). The variety of I. caduceus indicates a correla- (3) From a point 24 feet higher in the section, tion with the highest graptolite-bearing in thin-bedded limestones with shale partings, shales of Cow Head peninsula, Martin Point Didymograptus protobifidus of the type illus- and Lower Head, here considered to be of trated by Decker, 1941, occurs. This graptolite Whiterock age. These graptolites are of special is present in the high Canadian (Decker, 1941) interest because they date the beginning of and in the lower Chewton Series of Australia deposition of the green sandstones in St. Paul's (Harris and Thomas, 1938), the upper part of Inlet. At Martin Point and Lower Head the the extensus zone of the British Arenig Series Cow Head Group is overlain by considerable (Elles, 1933), and the upper part of the Lower thicknesses of green sandstone from which Didymograptus Shale of Norway (Monsen, fossils have not been obtained. At Cow Head 1937). the sandstones are not exposed. It seems likely (4) From shales interbedded with limestones that in the Cow Head area these green sand- 80 feet higher in the section: Tetragraptus stones are late Whiterock, or immediately post- serra. Whiterock in age. Similar green sandstones (5) From shales interbedded with limestones succeed beds of Table Head age in the Port au containing small brachiopod and trilobite Port peninsula and at Table Head (Schuchert fragments, 75 feet higher in the section (Oxley's and Dunbar, 1934, p. 72-73). unit 26): Isograptus caduceus cf. var. victoriae Green Island (Fig. I, A) between the Outer

PLATE 7.—CONTEMPORANEOUS DEFORMATION AT GREEN POINT FIGURE 1.—Two thin limestone beds contorted by submarine sliding, interbedded with undisturbed shales. Upper part of section at Green Point. FIGURE 2.—The same beds (as in Figure 1), showing surfaces. In upper layer the sharp crests of folds have fractured.

PLATE 8.—MIDDLE CAMBRIAN BEDS AT BROOM POINT FIGURE 1.—Bed A in left foreground, conglomerate bed C forming cliff (Fig. 7). FIGURE 2.—Fossiliferous conglomerate bed A overlain by fossil-bearing bedded limestones of bed B (Fig. 7). Lowest conglomerate bed is in foreground.

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and Inner Tickles was revisited, but no fossil- Another limestone conglomerate examined in iferous boulders were found in 1955. Here an 1955 was that making up White Point on the anticline plunging southward furnished John- south shore of St. Paul's Inlet (Fig. \,D). Here

•SE LS.CONGLOM BOULDERS UP TO 2 FT DIAM-SOME WITH MACLURITES

•GREEN SS. a RED SHALE ALTERNATING WITH DARK SHALE ISOGRAPTUS CADUCEUS Inlet

LS CONGLOM.

La WITH CHERT NODULES, ISOGRAPTUS CADUCEUS ENDYMIONIA, LJNGULA IOFT LS CONGLOM —BOULDERS

TETRAGRAPTUE SERRA

TETRAGRAPTUS FRUTICOSUSI 3 BRANCH) T. CF. SERRA PH/LLOGRAPTUS FIGURE 5.—ORDOVICIAN SECTIONS, ST. PAUL'S INLET A shows upper portion of the Cow Head Group interbedded with overlying green sandstone; B shows upper portion of the Cow Head Group on the east side of the Inner Tickle. son's Geological Survey of Newfoundland party two fossil-bearing boulders were found. One con- two boulders in 1938 which yielded: tained a large pygidium which seems to be Ctenopyge sp. Orria. This Middle Cambrian genus has not Bayfieldia idrichi been found previously east of the Rocky Rasetlia sp. Mountain area. The other boulder contained Zacompsus sp. the middle Cambrian genera Alokistocarc Stigmametopus sp. and Zacanthoides. This is an older fauna Punctuiaria sp. than any on Cow Head peninsula. It is com- Apatokephaloides sp. parable to that found on the White Rock Phylacterus sp. Islets and to the oldest fauna at Broom Point. Richardsonella sp. This indication of a Middle Cambrian age for Plethomelopus sp. this conglomerate is of interest because John- Onchonotus sp. son in 1938 assigned a Lower Cambrian age to ? Bellaspidella sp. the sandstones exposed in the next small stream This is a late Cambrian fauna, comparable to to the east (at the base of the falls from the that of bed 6 on Cow Head. Precambrian cliff).

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Martin Point Phylacterus. This is the Hungaia magnified fauna of the Upper Cambrian boulders of The beds exposed at Martin Point and their Levis and is equivalent to the fauna from bed thickness are indicated in Figure 6. The oldest 6 at Cow Head.

DlCHOGRAPTUS OCT08RACHIATUS ISOGRAPTUS CAOUCEUS VAR. VICTORIAE GLOSSOGRAPTUDfDYMOGRAPTUSS -2 SPP 'TETRAGRAPTUQUADRIBRACHIATUS S DIDYMOGRAPTUS NITIDUS

MAKT1N [CLONOGRAPTUS J [DlDYMOGRAPTUFLEXILIS »C.S RIGIOUS [DICTYONEMA sp. DlOYMOGRAPTUS — POINT EXTENS1FORM TYPE j SRYOGRAPTUS

STAUROGRAPTUS DICHOTOMUS DICTYONCMA sp.

-GRAPTOLITE FRAGMENTS (DICTYONEMA) [HUNGAILOeANOPELTOIDEA S KEITH I ELLA

FIGURE 6.—SECTION AT MARTIN POINT

beds are exposed along the north face where The graptolites Staurograptus dichotomus seven beds of limestone conglomerate are inter- and Dictyonema sp., representative of the Green beclded with dark shale and limestone. The Point Formation, were found 550 feet above conglomerate beds are 2 to 8 feet thick and the base of the section. consist of a mixture of flat fragments and Above this, slumped beds 1-2 feet thick rounded boulders. Fossils were found in the rounded boulders, mainly in those of white which grade up into overlying limestone con- limestone but also in those of brown, as well as glomerate were noted in thin limestones and in fine-grained mottled green and white lime- shales. Bent pieces of this type of limestone and stone. The fossils include Keithiella, Pseud- many flat slabs were seen in the overlying agnosius, Hungaia, Loganopeltoides, Theoden- conglomerate (PI. 5, fig. 1). A similar 1-foot- isiii, Loganellus, Aposolenopleura, and ? thick zone of slumped beds was seen below the

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lowest limestone conglomerate bed on the Oxley (1953, p. 13) recorded Isograptus from north side of Martin Point. this section, and Staurograptus dichotomus On the north side of the hogback forming a apparently only a short distance below it. This point a quarter of a mile south of Martin latter record seems to be in error. Point, 650 feet above the base of section, were found Dictyonema sp., Bryograptus sp., and Green Point Didymograpttis sp. of extensiform type. On the south side of the hogback point, 890 About 400 feet of beds, dipping southward at feet above the base of the section, were found 70°, are exposed at Green Point (PI. 3, fig. 2), Dictyonema sp., Clonograptusflexilis, C. rigidus, 6 miles south of Martin Point. Most of the and Didymograptus sp. of extensiform type. upper half of the section is dark shale, with Twelve feet higher in the section were found: some thin limestones and green and red shales, Tetragraptus quadribrachiatus, f Adelograptus with silts and sands in the higher part. In the sp., Bryograptus sp., and Didymograptus cf, lower half more limestones are present, and nitidus. there is a conspicuous 4-foot bed of limestone The absence of Tetragraptus approximates conglomerate near the point. The lowest few from both these higher graptolite-bearing tens of feet of beds on the north side of the point shales suggests that they may be a little older are thin-bedded dark-brown, bituminous shales than zone A of the Levis Shale (Raymond, which weather light gray and have interbedded 1914), and that they are pre-Deepkill Shale but limestones up to 1 foot thick. Certain bands of post-Schaghticoke Shale. A similarity between the bituminous shales are crowded with grapto- this assemblage and that of the middle Lance- lites, including Dictyonema flabellifortne s.l. field of Victoria, Australia (Harris and Thomas, (with rhabdosomes up to 15 cm in length and 1938), is evident. 15 cm wide), Staurograptus dichotomus Emmons, Higher in the section are several hundred Anisograptus cf. richardsoni Bulman, A. cf. feet of interbedded thin limestone and shale, matanense Ruedemann, and Bryograptus sp. dark and with some purple and green bands. Species of Dictyonema, Staurograptus, and Two beds of limestone conglomerate, each Anisograptus have been listed from here by about 3 feet thick, form conspicuous ribs on the Ruedemann (1947, p. 59; in Schuchert and shore. Dark gray and muddy green limestones Dunbar, 1934, p. 40). This shale is evidently of 20 feet below the second limestone conglom- about the same age as the Schaghticoke Shale erate yielded Isograptus caduceus cf. var. of New York and the shales of Matane and victoriae Harris, Dichograptus octobrachiatus Cap-des-Rosiers (Bulman, 1950). No fossils (Hall), two extensiform species of Didymograp- were found above these lower shales, except for tus, and Glossograptus sp. unidentifiable fragments of graptolites just This assemblage is about the same age as above the 4-foot band of limestone conglom- that found beneath the conglomerate at Lower erate. Thus the writers could determine no Head, in the highest shales on Cow Head, and in the highest beds in the section on the north upper age limit to the section at Green Point, side of the Inner Tickle, St. Paul's inlet. At and a Green Point Formation (or Series or some of these places I. caduceus of the maximo- Group) based on this section (Schucbert and divergens or divergens type occur, and following Dunbar, 1934, p. 38) is too vaguely defined to Harris' (1933) discussion, one might assume be of use. We therefore limit the term Green that these faunas were slightly younger than Point Formation to beds bearing the grapto- those with variety victoriae. However, both lites mentioned above. varieties occur together in the Inner Tickle In the section above the 4-foot conglomerate section, and hence only a general equivalence layer two thin limestone beds are thrown into of these highest beds of the Cow Head Series folds probably as a result of contemporaneous with Ca2 or Ca3 of the Castlemain Series of sliding (PL 7, figs. 1, 2). The crests of the folds Victoria (Harris and Thomas, 1938) can be in the higher limestone are broken, but the suggested. In the upper Deepkill Shale (Ruede- separate pieces are not dissociated. Dissociation mann, 1947, p. 350-353) and zone D2 of the of such fragments might provide the curved Levis Shale (Raymond, 1914), varieties of /. pieces of limestone and thin, flat pebbles seen caduceus are apparently not so conspicuous as in so many of the limestone conglomerates. they are in Newfoundland. Nevertheless, the Figure 1 of Plate 5 shows similarly disturbed upper Cow Head Group is of about this age. beds passing upward into conglomerate.

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Stearing Island probably exists between Stearing Island and Cow Head peninsula. Stearing Island includes a small, outer arc and a longer and wider inner arc, which makes Broom Point up the island proper (Fig. 1). The writers were able to make only two visits to these islands, Midway between Cow Head and Martin with insufficient time to examine all the out- Point is Broom Point (Fig. 1). The section crops even hastily, particularly since the south- studied lies between the mouth of Western western part of the inner island is accessible Brook and the anticlinal cove (Fig. 7). The only at low tide. The outer arc is apparently highest beds are thin-bedded limestones with formed by a single layer of conglomerate. From shale partings; most of the limestone is fine- boulders there the writers obtained the Middle grained, but some lenses are coarser in grain. Cambrian trilobites Olenoides, Solenopleura, Near the top are two conglomerate beds, one Parasolenopleura, and Welleraspis. about 4 feet thick. From a lens of coarser- This appears to be an older fauna than any grained limestone below this 4-foot conglom- found on Cow Head. Its age relative to the erate the writers obtained unidentifiable Middle Cambrian of the White Rock Islets trilobite fragments and inarticulate brachi- and of Broom Point is yet to be settled. opods. From a similar lens at about this level On the larger island more than one coarse (Fig. 7, G) came the Early Ordovician trilobites conglomerate band may be seen. Conglomer- recorded by Oxley (1953, p. 14-15) and later ates of small, flat limestone chips and layers of described by Rasetti (1954). These included dark shale with interbedded limestone are Bienwllia terranovica, Borthaspidella gaspensis, present. The succession dips southeastward in Leiobienvillia laevigata, Pareuloma brachy- the eastern part of the island and southward in metopa, and P. impunctata. Oxley (in Rasetti, the western part. The curved outline of the 1954, p. 581) mentions that dark argillites at island reflects this change in strike. From coarse this locality contain dendroid graptolites, but limestone conglomerates on the northwestern, the writers did not find any. From 50 feet below outer shore came boulders containing Hystri- these highest beds (Fig. 7, F), in a limestone curus sp., Symphysurina sp., aff. Pareuloma conglomerate layer about 10 feet thick (on the sp., cf. Parahystricurus sp., cf. Petigurus sp., south side of the small hill near the outlet of and f Psalakilus sp. These trilobites are like Western Brook), came boulders that contained those of the lower zones of Ross (1951) and the following trilobites: Parabolinella cf. Hintze (1953), and of bed 8 on Cow Head. triarthroides Harrington, an olenid, gen. indet., The conglomerate that runs along the south- ? Bellaspis sp., Hystricurus sp., Plethometopus eastern side of the island is about 30 feet thick; sp., Symphysurina sp., and Geragnostus sp. some of the boulders are 10 feet in length. Geragnostus, Symphysurina, and Parabolin- Trilobites from boulders in this conglomerate ella occur in the Morses line slate of Tremadoc include cf. Pseudagnostus sp., cf. Protopresbynil- age (Shaw, 1951, 1955). Parabolinella, Bellaspis, eus sp., aff. Goniophrys sp., Nileus sp., Carolin- and Plethometopus are found in the "Upper ites sp., Illaenus sp., Telephina sp., Glaphurina Cambrian" boulders of Levis (Rasetti, 1944, sp., Remopleurides sp., a cheirurid, and several 1945). These boulders at Western Brook may new genera. therefore be Late Cambrian, but the writers Some of these species are identical with those believe they are probably Early Ordovician in beds 9 and 10 of Cow Head peninsula, (Tremadoc). whereas Nileus and Telephina are characteristic The small hill consists of shale and thin of beds 12 or 14 of this succession. Ectenonotus limestones; below these is a considerable thick- and "Lichas" were not found, however, and it ness of thin and thick beds of limestones does not seem that any of the boulders on (calcarenites and muddy limestones) interbedded with shale and conglomerate layers. Stearing Island are as young as some of those Fossils came from two levels in these beds of bed 14. This conglomerate is underlain by (Fig. 7, D, E). The second conglomerate north dark-gray shales with interbedded limestones, of the hill produced boulders with Theodenisia but only unidentifiable graptolite fragments sp., Plethometopus sp., Stenopilus sp., Leio- were found in the shales. coryphe sp., Richardsonella sp., Stigmametopus The writers believe that interbedded con- sp., "Acidaspis" cf. ulrichi Bassler, and a ? glomerates and shales similar to those of Cow Ctenopyge spine. The sixth conglomerate north Head are exposed on Stearing Island. A fault of the small hill produced a similar fauna in-

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eluding Theodenisia sp., Plethometopus sp., Ptychagnostus cf. praecurrens, and Zacanthoides Stenopilus sp., and Leiocoryphe sp. It seems sp. best to refer these to the Late Cambrian This fauna contains a mixture of elements of rather than to the Early Ordovician. the Atlantic and Pacific realms. Stratigraph-

MENEVIELL8 A TOMAGNOSTUS PERONOPSIS HYPAGNOSTUS • KOOTENIA ] ZACANTHOIOES ORRIEULA AGRAULOS CORrNEXOCHUSPERONOPSIS- _

SECTION HJ FIGURE 7.—SECTION AT BROOM POINT H, north end of section in anticlinal cove; J, south end of section at mouth of Western Brook; A-G, fossil localities.

More limestone conglomerate beds, from ically it lies below the Atlantic realm Tomag- which no fossils were obtained, occur north nostus-Meneviella fauna. Whether it also is and down in the section. Beyond a covered equivalent to the Paradoxides hicksi zone of interval is a 50-foot limestone conglomerate Newfoundland and the Paradoxides paradoxis- bed (PI. 8, fig. 1; Fig. 7, C). Two boulders from simus zone of Sweden (Table 2) or is older will this yielded Meneviella iienulosa, Solenopleura be decided by further study of the fauna. sp., Corynexochus sp., Tomagnostus fissus, Below this fossiliferous limestone conglom- Hypagnostus truncatus, and Peronopsis sp. This erate is bedded brown granular limestone 3 feet fauna is the equivalent of the Paradoxides thick. This has furnished a Corynexochus hicksi zone of the Middle Cambrian of south- cephalon. Below this is a 15-foot limestone eastern Newfoundland. conglomerate which has yielded no fossils. Below this 50-foot bed of conglomerate is a 4-foot layer of dark shale which rests on 15 feet White Rock Islets of bedded limestone. Near the base of this limestone (Fig. 7, E) is a similar fauna (an Between Cow Head and Lower Head (Fig. original find of Oxley) which has Meneviella, 1) is a mile and a quarter of a narrow limestone Tomagnostus, Peronopsis and Hypagnostus. conglomerate island and underlying beds which Below this Middle Cambrian bedded lime- is covered in places by waves at times of high stone is a 5-foot limestone conglomerate which tide and wind. Waves and shore currents have has yielded many fossiliferous boulders (PI. 8, built a sand point almost to this island at fig. 2, A; Fig. 7, A). Among the trilobites are Downes Point. At the north end only limestone Agraulos sp., Bolaspis sp., Ehmania sp., Elrath- conglomerate can be seen. The lower part of ina sp., Koolenia sp., Orriella sp., Pagetia sp., the conglomerate with dolomite (?) blocks Peronopsis cf. fallax, Ptychagnostus cf. gibbus, seems to be unfossiliferous. The higher part has

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boulders up to 2 feet in length of white lime- shown in Figure 2 of Plate 6. Following Schu- stone, brown limestone, coarse oolite, and chert and Dunbar (1934, p. 78-79) the writers mottled limestone. Fossils in boulders at the interpret the white limestone at Lower Head as north end include Orriella and Olenoides. Other a single boulder in the conglomerate. An even Middle Cambrian boulders opposite Downes larger single boulder in the Levis conglomerate Point yielded ? Bathyuriscidella sp., ? Ehmania has recently been described by Osborne (1956, sp., Koottnia sp., f Solenopleura sp., ? Alokisto- p. 187-188). care sp., ? Glossocoryphus sp., and Olenoides sp. In the white boulder, fossils occur in concen- The Olenoides pygidium, which has two long trated patches, particularly near the geodes. lateral spines, resembles 0. schucherli from Trilobites are common, and brachiopods and eastern Gaspe. More Middle Cambrian fossil- large cephalopods also occur. The writers' col- iferous boulders were obtained at the south lections of 1955 and earlier ones by Kindle end of the White Rock Islets, in the upper 30 include the following trilobites: Trinodus sp., feet of conglomerates. Below this is 40 feet of *Bathyurellus nitidus Billings, *B. formosus conglomerate and dark-brown limestone, poorly Billings, Goniotelus sp., *"Illaenus" arcualus exposed and covered by weeds. Lithologically Billings, *7. tumidifrons Billings, */. consobrinus this lower portion is similar to the Arches, an Billings, Ischyrotoma twenhofeli Raymond, isolated outcrop on the shore 15 miles north- Perischodonus capitalis Raymond, an isocolid, northeast of Cow Head peninsula. There the a harpid, *Kawina vulcanus Billings, *Cheirurus limestone conglomerate contains some thin mei'curius Billings, and *"Lichas" juke-si Bill- slabs of dark limestone but is predominantly ings. made up of a brown granular porous limestone, Species marked by an asterisk were described which is primarily structureless but has a few by Billings (1861-1865), and the type specimens bedded layers 2 feet thick. in Ottawa are all in a white limestone and The fossils from the north, south, and central labelled as from Cow Head. The white lime- portions of the White Rock Islets show that stone is like that of the boulder at Lower Head, the islets consist of a Middle Cambrian con- and although these specimens could have been glomerate older than any of the beds exposed collected from a similar boulder in bed 14 on on Cow Head. They contain trilobites similar Cow Head peninsula, it seems far more likely to those from boulder bed A at Broom Point. that they came from Lower Head. This fauna Why the whole Cow Head sequence is not has usually been regarded as of Chazy age exposed shoreward is not known; perhaps a (e.g., Raymond, 1925, p. 166-167), but it may fault lies southeast of this outcrop. be slightly older, i.e., Whiterock. An upper limit to the age is suggested by the fossils in the Lower Head black shales and thin limestones on which the conglomerate is seen to rest in the first small Observations at Lower Head and along the cove north of Lower Head (Fig. 8, A; PL 5, coast a short distance north are summarized in fig. 2). Graptolites in the shales include Dicho- Figure 8, and an interpretation of the structure graptus octobrachiatus (Hall), Tttragraptm cf. is offered in the cross section. At the tip of bigsbyi, Phyllograptus cf. ilicifolius, Didymo- Lower Head is an unbedded mass of white graptus sp. of protobifidus type and Isograftus limestone, which is irregularly fractured and caduceus cf. var. divergens Harris. The presence contains calcite-filled geodes. The mass is of /. caduceus indicates a high Deepkill or high about 600 feet in length; the scalloped margin Levis shale age, or Castlemain of Australia, is exposed on the west side, where it is in con- and thus post-Canadian age. On the opposite tact with other boulders of this exceptionally (west) side of this cove are black shales, cherts, coarse conglomerate (PI. 4, fig. 2). However, and thin limestones (Fig. 8, B) containing along the shore northeast from Lower Head, Dichograplus octobrachiatus (Hall), Tctragraptus the mass is replaced by coarse limestone con- cf. bigsbyi, Phyllograptus cf. ilicifolius, Didymo- glomerate; after another covered interval, graptus sp. (wide horizontal stipe), and ? green sandstones are exposed. Northward along Isograplus sp. the shore toward the first small cove, conglom- These seem to be of the same age, and the erate is exposed and includes several gigantic writers suggest that they are inverted and blocks between 50 and 200 feet in length. One underlie the conglomerate immediately to the of these is packed with large gastropods (? west. This conglomerate has big blocks of Madiirites sp.). The general appearance of the limestone, some of which contain gastropods, conglomerates between the large blocks is and looks like the conglomerate at Lower Head.

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Beyond the point made by this conglomerate The green sandstones are considered to be is a smaller cove, along the west side of which the same age as those east of Lower Head, i.e., conglomerate crops out. Northward along this Middle Ordovician, and must be separated by a

FIGURE 8.—ROCKS OF LOWER HEAD A, B, C indicate graptolite localities; M represents boulders with Madurites sp.

outcrop the conglomerate forms a ridge a short fault from the contorted black shales and lime- distance inland, which runs subparallel to the stones with graptolites. shore. On the shore black shale, thin limestone, and interbedded cherts are isoclinally folded; DISCUSSION OF STRATIGRAPHY they are replaced seaward by outcrops of green sandstone. From the black shales (Fig. 8, C) Nomenclature of Covj Head Group graptolites of Levis shale zone A (or middle Lancefield, La2, of Australia) were obtained. The term Cow Head Group is here used for They include: Dictyoiicma sp., Clonograptus about 1000 feet of limestones with interbedded flexilis, Telragraplus approximatus, Tetragrap- shales and limestone conglomerates; the lowest tus quadribrachialus, Phyllograptus cf. angmti- strata are of Middle Cambrian age, the young- jolius, Didymograptits cf. nilid-us, and Didymo- est early Middle Ordovician (Whiterock Stage). graptus sp. The name Cow Head Limestone Breccia was

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first applied to the exposures on Cow Head Ruedemann's list from "St. Paul's Inlet and peninsula by Schuchert and Dunbar (1934, p. other localities" (1947, p. 59) seems to include 73). The writers give the name group rank and graptolites from all these beds but no fauna as extend its meaning to include older rocks near young as Normanskill. Oxley (1953, p. 17-27) the original type exposures. This procedure attempted to use the term St. Paul Group for avoids the introduction of new names, and no what the writers call the post-Green Point name used previously is either as suitable or as Formation portion of the Cow Head Group, readily adaptable. The terminology used here is but was unable to work out a zonal sequence of compared with that of earlier authors in Ta- graptolites. It seems clear that such a sequence ble I. can be worked out and recognized in different Schuchert and Dunbar (1934, p. 38-40) outcrops. A detailed examination of the introduced the name Green Point Formation stratigraphy around the shores of St. Paul's (or Green Point Series) for the shore exposures Inlet is necessary before a name based on these at Green Point, about 18 miles south south- exposures can be adequately defined. The west of Cow Head. The writers were able to name is not used because such information is find abundant fossils only in a few feet of shale not available, and because at least some of the in the lower part of these exposures; these were rocks in St. Paul's Inlet are of the same age as of the Staurograptits-Dictyonema fauna first part of the Cow Head Group. made known here by Schuchert and Dunbar. Johnson (1941, p. 143) also proposed a West- Frequent references have been made to these ern Brook Pond Group, presumably for expo- graptolites (e.g., Rucdemann, 1947, p. 59; sures along the shores of this pond. Johnson Bulman, 1950, p. 67; Dunbar in Twenhofel states that this group of graywackes, sand- et al., 1954, p. 271), and the writers here limit stones, black shales, and cherts, 4000-5000 the name Green Point Formation to the zone feet thick, yields graptolites of lower Deepkill yielding this characteristic Early Ordovician age. According to Ruedemann (1947, p. 60) fauna. Oxley (1953, p. 12-17) used the term the graptolites from these rocks are similar to Green Point Group, employing as a standard those of the St. Paul Group. Oxley (1953, p. the sequence of strata from the north face of 18) states that Johnson has abandoned the terra Martin Point southward about half a mile. We Western Brook Pond Group. Again, until the reinvestigated this section (Fig. 6) and believe stratigraphy is better known the term can that it displays beds ranging in age from Upper hardly be used or even adequately defined. At Cambrian to early Middle Ordovician, i.e., the outlet of Western Brook Pond many speci- equivalent to a large part of the Cow Head mens of Isograptus sp. were collected from Group. This seems an unwarranted extension dark shales in a series of limestones and inter- of the term Green Point, but the section does bedded dark shales, red and green shales, and include the Green Point Formation as here limestone conglomerates. Thus at least some restricted. Johnson (1941, p. 144) earlier used of the rocks exposed around the shores of West- the term Green Point Group and described the ern Brook Pond are of late Cow Head Group ±1700 feet as "intercalated black to gray age, as are some of those in St. Paul's Inlet. shales, sandstones and thin-bedded dolomites The strata underlying the Cow Head Group or limestones, with breccia." No type section are not displayed within the region here in- was designated, though this description may vestigated, nor are the overlying beds seen on refer to the section at Green Point. Unless Cow Head peninsula. However, at Martin fossils other than those at the base of the sec- Point, at Lower Head, and in St. Paul's Inlet, tion are found, the group term can hardly be beds with Isograptus are succeeded by coarse used away from Green Point. green sandstones. These sandstones were Johnson (1941, p. 143) introduced the term thought to be in faulted contact with the under- St. Paul's Group, presumably for exposures in lying limestone conglomerates, limestones, and St. Paul's Inlet, 600-1000 feet thick, of "black shales at Martin Point (Oxley, 1953, p. 13) and shales, interbedded with thin limestones and Lower Head (Schuchert and Dunbar, 1934, p. sheets of breccia or intraformational conglom- 79-80). However, a gradational passage be- erate" containing upper Deepkill and basal tween the two is seen immediately west of the Normanskill graptolite faunas. The writers outlet of Black Brook, in St. Paul's Inlet found graptolite-bearing beds from upper (Fig. 5, ^4). From dark shales interbedded with Tremadoc (Clonograptus) to early Middle green sandstones and red shales, and overlying Ordovician (Isograptus) represented in the two a limestone conglomerate, came the graptolites sections examined in St. Paul's Inlet (Fig. 5). Isograptus caduceus cf. var. divergens Harris,

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Tetragraptus cf. similis, and Didymograptus given. Oldest of the faunas is that of the Green sp. This is the Isograptus fauna of the highest Point Formation, found on Cow Head penin- Cow Head Group, and its occurrence at the sula, at Martin Point, and the type locality. base of the green sandstones suggests that these About 100 feet higher in the section at Martin sandstones succeed the group in normal se- Point are black shales which contain species of quence. Oxley (1953, p. 34) referred these Dictyonema and Bryograptus. Black shales 250 sandstones to the Humber Arm Group and feet higher yielded these fossils and species of also thought, with some reservations, that they Clonograptus and ? Adelograptus. Neither succeeded the Cow Head Group normally. The Tetragraptus approximates nor phyllograptids present evidence supports the view that the was found in these strata; hence they probably sequence is a normal one. belong to an older zone than do such layers as Schuchert and Dunbar (1934, p. 72-73) bed 8f and basal bed 9 on Cow Head peninsula, tentatively correlated the green sandstones which yield T. approximates, abundant phyllo- succeeding the limestone conglomerate at graptids, and Clonograptus, but not Bryograp- Lower Head with the upper Long Point Series. tus. This Clonograptus-Bryograptus zone of On the basis of the brachipods the Long Point Martin Point has not been recognized elsewhere, Series is regarded as of Upper Wilderness age but the T. approximates zone has been found in (Schuchert and Dunbar, 1934, p. 72; Cooper, St. Paul's Inlet and also 1 mile north of Lower 1956, p. 13) or upper Normanskill, far younger Head. than the Isograptus beds of Whiterock age. The next graptolite-bearing shale found on Thus the name Long Point is not used for the Cow Head peninsula (but not recognized in sandstones of the Cow Head region, not only other sections) is that with Tetragraptus fruti- because of the difference in age, but also cosus having four stipes. It is a characteristic because the Long Point Series is stratigraphi- fauna of the lowest part of the type Deepkill cally isolated and crops out 95 miles southwest and of Levis zone B (Raymond, 1914). The on Port au Port peninsula. The writers do not rhabdosomes of T. fruticosus type collected at support Oxley's use of the name Humber Arm the Inner Tickle, St. Paul's Inlet, seem to have for these sandstones. The type section of this only three stipes; in the same layers is a species series (Schuchert and Dunbar, 1934, p. 86-89) of Didymograptus similar to some that have is 60 miles south of Cow Head peninsula; the been called D. bifidus. Slightly higher in the rocks are shattered and crumpled, and no fos- section D. protobifidus is common. These two sils have been described from the type section faunas are placed in a single zone, the three- (Walthier, 1949, p. 23-26). A new name for stipe T. fruticosus recalling the higher part of these sandstones is not introduced because the Bendigo Series of Victoria, and D. protobi- their stratigraphy is not yet known. Deposition fidus equivalents of the Chewton Series. These of these sandstones seems to have begun in two zones have been recognized only in St. late (?) Isograptus zone time, and Oxley (1953, Paul's Inlet. In all sections, below the highest p. 34) notes the considerable thickness of these conglomerates of the Cow Head Group, are elastics. If the Normanskill graptolites re- varieties of Isograptus caduceus like those of corded by Ruedemann (1947, p. 60, lines 12- Australia (Harris, 1933). The varieties of I. 21) come from this same series in the neighbor- caduceus occur with different assemblages in hood of Portland Creek Pond (22 miles north- different places, e.g., with Trigonograptus in bed east of Cow Head), then deposition must have 13 on Cow Head peninsula and with Dichograp- continued at least into the Porterfield Stage. tus octobrachiatus at Martin Point and Lower Head. Also the varieties do not occur in the Zonation and Correlation with Other Areas same sequence in time as in the Castlemain Series of Australia; there Trigonograptus ap- Suggested zonal divisions of the Ordovician pears in the succeeding Yapeen Series (Harris part of the Cow Head Group, occurrence of the and Thomas, 1938). Thus the Isograptus zones in various sections, and correlations are caduceus zone is a broad one, which cannot at summarized in Figure 4. The graptolite zones present be subdivided, and is evidently equiva- are broadly conceived on the basis of the suc- lent to Raymond's zone DI at Levis and the cession of faunas recognized, but since the highest part of the type Deepkill shale. graptolites have been found only in thin beds Although the graptolites have been collected and interbeds of dark shale, the thickness and from bedded strata, all the trilobites are from limits of each zone cannot be defined. However, conglomerate boulders on Cow Head peninsula approximate total thickness of the sequences is or at Lower Head. Comparison with other

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areas, and particularly with Ross' (1951) and fossils are known from the upper part of this Hintze's (1952) work in Utah and Nevada, zone in Britain (Elles, 1933), and because shows that the trilobites from successively Isograptus is abundant at a slightly higher higher conglomerates are stratigraphically horizon in Norway (Spjeldnaes, 1953). On the younger. In addition, the boulders in any partic- other hand, possibly D. protobifidus and /. ular conglomerate can hardly be much younger caduceus appear earlier in Europe than else- than the strata on which that conglomerate where, and the great burst of varieties of 7. rests, though they may be somewhat older. The caduceus in North America and Australia may trilobites listed in Figure 4, then, may be be later, as late as Llanvirn time. The basis for regarded as only approximately the same age as this suggestion lies in the apparent equivalence the graptolites shown to correspond. Some of Whiterock trilobites (Nileus, Remopleurides, interesting points emerge from this tentative Bathyurellus, Ectenonotus) with the /. caduceus correlation. As has been discussed previously, zone. It seems difficult to accept middle Arenig genera known from the Upper Cambrian age for these trilobites and reconcile this with Hungaia magnified fauna of the Levis boulders views expressed elsewhere on correlation occur in conglomerates 50-100 feet above the between the British and North American Green Point Formation; in some boulders they Ordovician (Whittington, in Twenhofel et al., occur with Tremadoc genera. Thus some of 1954); Llanvirn age seems more probable. these genera may range higher than has been Confirmatory evidence that the Whiterock supposed but perhaps not above the middle Stage limestones of the Table Head may be of Tremadoc. Trilobites of middle and upper Isograptus zone age is offered by graptolites in Lancefield (and also middle and upper Trema- shale overlying these limestones at Black Cove, doc) age include some genera that occur in about \y% miles northeast of the gravels at Ross' and Hintze's zones B to E, and also Port au Port peninsula (Schuchert and Dunbar, Ampyx sp. This genus appears commonly in 1934, PL 7, A). The collection of these grapto- beds of Porterfield age in North America but lites includes Didymograptus sp., Isograptus cf. was not recorded from the older strata studied forcipiformis (Ruedemann), Cardiograplus craw- by Ross or Hintze. Species do occur in the fordi Harris, ? Skiagraptus, Glyptograptus cf. Lower Ordovician McKay Group of British dentatus, and Glossograptus hincksii and is of Columbia (Kobayashi, 1955), and Whittington upper Yapeen age, i.e., a zone immediately recognized one in C. W. Merriam's collections above the Isograptus zone of the highest part of from the Ninemile Formation of the Pogonip the Cow Head Group. Dunbar (in Twenhofel Group (Nolan, Merriam, and Williams, 1956, et al., 1954, p. 255) also listed some of these p. 27). Some of the genera in the highest con- genera from this locality. glomerates are common to the Whiterock The sequence of Cambrian faunas is shown in Stage, and these boulders are derived from Table 2. The oldest of these occurs in a 5-foot rocks that may be the same age as at least part conglomerate at Broom Point (Fig. 7, A}. of the Isograptus caduceus zone. Here are found Agraulos, f Bolaspis, Kootenia, The graptolite faunas of the Cow Head Group Zacanthoides, Orriella, Peronopsis, and Ptychag- and New York and Quebec formations are noslus cf. gibbus. This may be equivalent to the evidently similar, and their likeness to those of Ptychagnostus gibbus zone (Bl) of Sweden the Australian sequence is remarkable. This (Westergard, 1946). In the bedded limestone resemblance is far greater than that to any of above this occurs Meneviella, Peronopsis, the zones of Britain or Scandinavia; the at- Hypagnostus, and Tomagnostus fissus which tempt to correlate with Britain raises problems. must be correlated with the Tomagnostus fissus Harris and Thomas (1938) regarded the Lance- zone (B2) of Sweden and with the Paradoxides field and Tremadoc as equivalent, but it is hicksi zone of southeastern Newfoundland. suggested, on the basis of the supposedly The Dresbachian faunas have been inter- equivalent trilobites, that the top of the Tre- preted as the equivalent of the Paradoxides madoc should be placed lower down. A different forchhammeri zone of the late Middle Cambrian opinion is also expressed as to the position of (Lochman, 1956; Wilson, 1957). Following this the Arenig-Llanvirn boundary. Harris and suggestion the writers place the Cow Head Thomas placed this boundary well above the Dresbachian in the Middle rather than in the Yapeen Series and regard strata with D. pro- Upper Cambrian. Beds 1 to 4 on Cow Head tobifidus and Isograptus caduceus as equivalent are then to be correlated with the Paradoxides to the upper part of the extensus zone of the forchhammeri stage of Sweden and more par- Arenig. This seems to be because both these ticularly with the Solenopleura brachymetopa

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zone (C2) if one follows Wilson (1957). Above this dating. Present knowledge indicates that this is the Taenicephalus faunule which is cor- this predominantly dolomite-limestone facies related with the Conaspis zone of the Franco- was deposited during the same span of time as nian of the mid-west and possibly with zone 4 of the Cow Head Group and attained a thickness the Olenid Series of Sweden. The succeeding 2 or 3 times as great. Whether deposition of Hungaia magnified fauna of Bed 6 at Cow Head this facies was continuous or not is uncertain. is to be correlated with zone 5 of the Olenid The writers tentatively conclude, then, that Series of Sweden because of the presence of to the east of the Cow Head Group facies a Ctenopyge. limestone-dolomite facies was being deposited during at least part of the same time. Relation of Cow Head Group to Other Sequences Not enough is known of the thicknesses and distribution of the Cow Head Group conglom- Johnson (1941) was the first to recognize the erates to guess the geographical position of existence of two facies in the Ordovician rocks the area from which the boulders may have of this region (Table 1): one of the St. George- been derived. Cambrian and Early Ordovician Table Head series, the other the types of rocks limestones of the lithological types and fossil exposed at Green Point and along the shores of content of these conglomerates are unknown in St. Paul's Inlet and Western Brook Pond. place in western Newfoundland. Some of the Rocks of age equivalent to the Cow Head Group upper Canadian and early Middle Ordovician are best known from the Port au Port peninsula, limestone boulders, however, contain fossils about 105 miles southwest of Cow Head. In identical with those known from the St. George this area the sequence includes Middle Cam- or Table Head Series which crop out 50 miles brian sandstones, shales, silts, and dolomites or more northeast. Possibly deposition in this (Schuchert and Dunbar, 1934, p. 33-35; general area of a third facies, at least in Middle Lochman, 1938); the fossils come from the and Upper Cambrian times, supplied the lime- upper 750 feet of dolomites and siltstones. stones now included in the conglomerates. Succeeding these beds are about 2000 feet of Conglomerates of the Cow Head Group type the St. George Series of dolomites, limestones, (i.e., intraformational in origin) are present in sandstone, and siltstone (Schuchert and the upper Table Head rocks of the Port au Port Dunbar, 1934, p. 45-51). Upper Cambrian area and northward beyond Cow Head to fossils have not been discovered in these rocks, Daniel's Harbour and perhaps even to Pistolet and those fossils described from the St. George Bay (Schuchert and Dunbar, 1934, p. 81). The Series are seemingly from the upper part and of limestone conglomerates at Levis, Quebec, and upper Canadian age (e.g., Ulrich et al., 1944, along the south shore of the St. Lawrence p. 21-22; Whittington, 1953, p. 658, 660-661). contain boulders of Cambrian limestones The overlying early Middle Ordovician Table remarkably similar in lithology and fossil Head Series includes about 800 feet of dark- content to those of the Cow Head area. Thus the gray limestone with black shale at the top. The facies from which these boulders were derived is Middle Cambrian to Middle Ordovician se- not a purely local phenomenon but one that quence of Port au Port is thus on the order of extended (not necessarily continuously) about 3500 feet thick and consists primarily of 800 miles along the strike. That these two or dolomites and limestones. This series of rocks three facies were not separated from each other forms the coast line from Cape Norman at the by any great distance or barrier is indicated by Strait of Belle Isle south to Table Head. From examples of their intertonguing—e.g., intra- there to the Port au Port peninsula it is found formational conglomerates in the Port au Port a short distance inland (in bays and inlets), area, upper St. George-type boulders in the discontinuously exposed at the foot of the Long conglomerates, and the occurrence at Broom Range (Schuchert and Dunbar, 1934; Wal- Point of bedded limestone with the same thier, 1949; Oxley, 1953). The lithology is trilobites as in the boulders of the overlying predominantly dolomites and limestones, but conglomerate. It does not seem necessary to the dating of parts of the sequence and of suppose that these facies everywhere were particular exposures in various areas is vague deposited in the same geographical relationship or unknown. Oxley (1953) mapped St. George to each other, i.e., ran in linear bands along the and Table Head dolomites and limestones as strike, one always east or west of the other. running along the foot of the Long Range 4 or 5 They might occur sporadically, depending on miles east of the type area of the Cow Head tectonic, sedimentary, and oceanographic con- Group but identified no fossils to substantiate ditions prevailing in particular areas.

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Origin of the Conglomerates the size of the blocks but because, for example, in bed 3 on Cow Head bedded limestones pass Contrary to Schuchert and Dunbar's views, laterally into conglomerates (PL 1, fig. 1), and the writers believe the evidence to be conclusive at Broom Point limestones of the same type that the conglomerates of the Cow Head Group as seen in certain boulders directly underlie the were not all formed at the same time in direct conglomerate. It seems necessary that the connection with Middle Ordovician thrusting. source area, after deposition and lithification, Rather, the conglomerates are intraformational must have been raised and broken to produce and originated at intervals during the long the larger blocks, though the chips might have span of time from Middle Cambrian to early been produced by slumping and consequent Middle Ordovician. They are intercalated breaking up of thin limestone layers (PI. 7, within a surprisingly thin (±1000 feet) se- figs. 1, 2; PL 5, fig. 1). The blocks and boulders quence mainly of limestone and shale, and each must have slid down a submarine slope as King layer is about the same age as the strata on (1951, p. 84) was the first to suggest. which it rests. The conglomerates consist of The uneven base of some layers, the wedging beds of small, flat chips (PI. 5, fig. 1) in which out of layers, and the cross-cutting relationship there may be scattered large blocks, or of of the base of bed 12 at The Ledge on Cow Head angular and subangular boulders (a few inches peninsula (PL 1, fig. 2), all support this view. to 600 feet in length) in a muddy (rarely sandy) Occasionally a boulder seems to have travelled matrix (PI. 6, fig. 2). Blocks of interbedded alone, or rolled on ahead of a slide (PL 4, fig. 1). limestone and shale, usually folded, may occur The same general mode of origin of the Levis (PI. 6, fig. 1), and rarely lumps of chert, shale conglomerates has recently been advocated by or siltstone. Most of the boulders and chips are Osborne (1956, p. 185-187). The writers do not limestone, and no igneous or metamorphic think the boulders in the Cow Head Group material was seen. No petrological studies of came from cliffs of great height because such either the boulders or the matrix were made, an origin should provide boulders of a wider and the fossil collections were generally from stratigraphic range than we find in any one the larger fragments. This is because such layer. However, a submarine fault of minor boulders generally project from the weathered displacement could initiate a submarine land- surface of exposures, and can be more readily slide which would include strata of a limited broken, whereas the layers of small chips tend horizon only. to weather to a smooth surface. Perhaps one in The direction of movement of the boulders thirty of the larger blocks contain fossils, and cannot be surmised from the available evidence. it was soon discovered that in any one con- It seems at least possible that the limestones glomerate layer, limestones of a certain color or were laid down on the crests of sporadically texture were generally unfossiliferous, whereas distributed ridges. Presuming these ridges to others were generally the reverse. All this points be elongated in the north-northeast to south- to the source of the conglomerates being a southwest direction of the present stride, sliding region of limestone deposition, the limestone off them might have been in either direction— varying in color and texture to include cal- east or west. For the Levis conglomerates carenites, oolites, calcilutites, and dense fine- Osborne (1956, p. 197-198) prefers an origin grained, varicolored porcellanous limestones from the south, particularly because Late (thin- and thick-bedded), sometimes with Ordovician thrusting is from this direction. shale partings, and also including unbedded Since the Levis and Cow Head conglomerates masses of light-colored biohermal (?) type. seem to be related phenomena, and since the Deposition must have been continuous from thrusting at the foot of the Long Range in Middle Cambrian to Middle Ordovician time, western Newfoundland is from the east, one with relatively rapid lithification, in order that might go on to assume that the Cow Head the boulders may rest on rocks of similar age. conglomerates moved in from the east, as a As has been discussed in the preceding sec- result of earlier tectonic movements producing tion, the known Middle Cambrian rocks of linear welts. This may or may not be so, but Port au Port peninsula and parts of the dolo- it seems that the evidence now available is not mitic Lower Ordovician St. George Series are decisive. hardly suitable as a source for the conglom- From his observations near Portland Creek, erates, and thus the source limestones may 20 miles north of Cow Head, Nelson (1955, represent a separate facies. This facies cannot p. 44) was "inclined to attribute the formation have been far distant, not merely because of of the breccia to localized earthquakes affecting

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semi-consolidated limestone muds. These shocks which have come down from shallower environ- would partially fragment the limestone so as ments. to give an interlocking texture. . . . Exotics Future work alone can determine whether would be considered as fragments of overlying this is a regular stratigraphic sequence of and underlying rocks incorporated in the conglomerates unique to this region or is found breccia during its formation." in other limestone conglomerates of the St. The nature of the Cow Head Group strata is Lawrence valley. It is interesting to see what well explained in an article on Flysch sedimenta- has been written of the conglomerates and tion by Sujkowski (1957) whose field work was associated beds at Levis and Quebec. Of the done in the Carpathian mountains of central Sillery [Charny], Bailey et al. (1928) say "the Europe. A few of his sentences may be quoted: fossiliferous limestone boulders of the Sillery conglomerates are exclusively Cambrian; al- "The name Flysch is a fades denomination for a most all of them are of Lower Cambrian date." marine deposit composed of innumerable alterna- tions of sharply divided pelitic and psammitic Above the Charny, Osborne (1956) places the layers. Other rocks in the deposit are accidental, Lauzon Formation in which Middle Cambrian and in particular pure limestones are rarely present. fossils have been found in boulders. Boulders The series commonly attain thicknesses of thousands from the overlying Levis Formation "include of feet and were deposited in geosynclinal areas. The pelitic layers are composed of either calcareous a few of Lower Cambrian and a profusion of or noncalcareous shale; the psammitic layers are Upper Cambrian and Beekmantown date" chiefly sandstone, but mudstones, arkoses, con- (Bailey et al., 1928). The younger Quebec glomerates, and gravel beds are also found. ... If City Formation has shales with graptolite remains of micro-organisms exist in a shale layer neighboring a fossil-bearing psammitic layer, the faunas of mid-Trenton age and contains fos- fossils in the shale differ from those in the psammite siliferous boulders of Black River and Lower and in most cases have siliceous instead of calcare- Trenton age though these fossils "are not of ous skeletons. The shell detritus and the forami- the same character as the fossils found in nifera seem to have been brought with the coarse material from outside the site of deposition. ... It Canada in these formations northeast [north- was never possible to identify layers from different west] of the Champlain-St. Lawrence thrust." profiles by their thickness: sandstone beds especially (Bailey et al., 1928) There seems to be a could not be compared even in two profiles across regular stratigraphic sequence except for the the same tectonic unit 1 mile apart. . . . the average rate of deposition [of the shale portion isl 0.8-1.0 Levis Formation in which "at least nine conglom- inches per 1000 years. The average thickness of the erates could be distinguished." It would be individual layers is about 5 inches. Thus a sandy interesting to know if the mixture of Cambrian phase occurred about every 4000 years. . . . The permanently unstable condition of the slope, with and Ordovician fossiliferous boulders occurs in slides occurring at more or less regular intervals all nine of these conglomerates. Whatever over millions of years, indicates some tectonic move- future studies may show of the stratigraphy of ment in the basin itself, or at least some steady subsidence of the lower end of the slope. Subsidence the Levis conglomerates their similarity to those was uniform rather than rhythmic, but a steady of the Cow Head region is striking and their steepening of the submarine slope caused breaks of origin may be similar. For the Cow Head Group equilibrium and in consequence submarine landslides at rhythmic intervals. . . . Each landslide of we concur with Bailey, Collet and Field (1928) soft sediment moving down the slope might become in their observation on the Levis conglomerates a turbidity current; each spread a layer of psammitic "We hold that the limestones. ... of the one deposit at the bottom of the slope and made a future lens of sandstone. . . . Flysch is a fades facies were intermittently discharged as land- characterized by both monotony and variability. slips down a submarine slope on to the muds of The pelitic (monotonous) element represents the the other facies." indigenous deposit; the psammitic (variable) element is exotic. The nature of the pelitic layers and the required mechanism for the introduction of the REFERENCES CITED psammitic layers make it clear that Flysch was deposited in a deep-water environment." Billings, E., 1861-1865, Paleozoic fossils: Canada Geol. Survey, v. 1, p. l-i26, 401 Figs. Bailey, E. W., Collet, L. W. and Field, R. M., 1928, If the sandstone beds had been limestone Paleozoic submarine landslips near Quebec City: conglomerate beds, Sujkowski's description Jour. Geol., v. 36, p. 577-619 would have fitted the Cow Head Group. It Bulman, O. M. B., 1950, Graptolites From the helps explain why fossils other than graptolites Dictyonema shales of Quebec: Geol. Soc. London Quart. Jour., v. 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F., 1956, Geology near Quebec City: CITY COLLEGE OF NEW YORK, NEW YORK 31, Le Naturaliste Canadian, v. 83, p. 157-224 NEW YORK Oxley, P., 1953, Geology of Parsons Pond-St. Pauls MUSEUM OF COMPARATIVE ZOOLOGY, CAMBRIDGE area, West Coast: Newfoundland Geol. Survey 38, MASSACHUSETTS Rept. 5, 53 p. MANUSCRIPT RECEIVED BY THE SECRETARY OF THE Rasetti, F., 1944, Upper Cambrian trilobites from SOCIETY, JUNE 12, 1957

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